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XRD analyses show that the sediments from Sites U1325–U1329 are dominated by detrital minerals, mainly quartz, feldspar (plagioclase and potassium feldspar combined), mica, and clay minerals (Table T1). Carbonates are only minor components constituting <5 wt%, with low Mg calcite as the dominant phase. Dolomite is generally rare, and aragonite is absent at the detection limit. Because of the inhomogeneous nature of the sediment (Expedition 311 Scientists, 2005) the mineralogical composition varies considerably between adjacent sampling depths and also between adjacent holes of one site (cf. Site U1329). Nevertheless, the overall mineralogical trends reflect the lithostratigraphic division applied for each site, as described in the following (in southwest–northeast succession).

At Site U1326, situated at the southwest end of the transect, low calcite content discriminates lithostratigraphic Unit II from Units I and III, which contain more calcite (Fig. F1). This conforms with low microfossil contents in Unit II compared to those in Unit I and III. Grain size variations are less prominent than at Site U1325 (see the “Site U1326” chapter, this volume); thus, changes in the mineralogy are less distinct, although a trend toward higher illite and chlorite contents in the lower Unit II and entire Unit III can be observed.

Site U1325 is situated in a slope basin near the southwest end of the transect cored during Expedition 311 and comprises four lithostratigraphic units (see the “Site U1325” chapter, this volume). As expected from the basinal setting, turbidites are frequent throughout the cored sections. Unit I is divided into Subunit IA, consisting of sand-rich deposits with abundant quartz and feldspar, and Subunit IB, dominated by fine-grained sediments with high illite and chlorite contents. Grain size and mineralogy are apparently closely coupled in both cases (Fig. F2). Unit II is distinguished from Subunit IB by the absence of diatoms, sponge spicules, and foraminifers as well as low calcite and illite contents. In Unit III, where biogenic components are more abundant, calcite increases again and finally drops to very low values in Unit IV. The maximum amounts of calcite found in Subunit IB and Unit III correspond to high amounts of biogenic components, including calcareous microfossils such as foraminifers. The calcite content may therefore originate mainly from calcareous microfossil remains.

At Site U1327, located midslope of the accretionary prism, the most prominent variations are recorded in the illite content (Fig. F3). Lithostratigraphic Unit I (clay and silty clay interbedded with coarse silt to gravel-sized layers) has fluctuating low to high illite contents, which are more constant on a relatively low level in Unit II (clay to silty clay with diatoms and interbedded sandy silt and sand layers) and increase again in Unit III (silty clay with diatoms in the lower part). The calcite content is low throughout the record. In both Units II and III dolomite was observed regularly, although in minor amounts.

Site U1328 is located at the Bullseye vent site, within an area of active cold vents. The bulk of the emanating methane gas is thought to be transported along isolated feeder channels or fractures toward the seafloor (Riedel et al., 2006), leading to a massive accumulation of gas hydrate in the upper ~40 m of the sedimentary column (see the “Site U1328” chapter, this volume). The mineralogy of this zone is marked by a relatively high quartz abundance and a zone of very high chlorite and illite contents between 25 and 35 meters below seafloor (mbsf) (Fig. F4); small amounts of dolomite are present occasionally. Although steeply dipping structural features are common in the upper 40 m of the sedimentary column, the mineralogical variations between Holes U1328B, U1328C, U1328D, and U1328E are relatively small (Fig. F4). The mineralogy of Site U1328 below 40 mbsf is quite variable because of the abundance of turbiditic deposits. Lithostratigraphic Unit I (turbidite and sand rich) and Unit II (fine-grained, microfossil-rich sediments) are mainly differentiated by higher illite and calcite ratios in Unit II relative to Unit I. Quartz contents do not follow the lithologic units very closely but show a more cyclic pattern with contents that are high at ~30 mbsf, decrease until ~100 msbf, increase again in the lower Unit I and upper Unit II, and decrease to a second low at the Unit II/III boundary. Quartz remains on a moderate level in Unit III after an initial increase. The mineralogical composition of samples from Unit III (abyssal plain deposits with very few turbidites) shows a lower variability than the turbidite-rich Units I and II. Notable are relatively high calcite contents and the frequent occurrence of minor amounts of dolomite. The calcite content at Site U1328 might partly reflect biogenic components but possibly also dispersed authigenic precipitated calcite crystals, especially near the bottom-simulating reflector and in the gas hydrate accumulation zone in the upper 40 mbsf.

From Site U1329, located at the eastern limit of the gas hydrate occurrence on the northern Cascadia margin, active dolomite formation is reported (see the “Site U1329” chapter, this volume); thus, the high dolomite contents (in relation to the lower part of the cores) observed in Unit I (Fig. F5) might be caused by authigenic dolomite precipitation. Also clearly visible is the hiatus between upper Miocene (Unit III) and Pleistocene (Unit II) deposits, accompanied by a drop in feldspar, chlorite, calcite, dolomite, and less pronounced, illite contents. The low frequency of turbidite deposits in Unit III is reflected by a rather constant mineralogical composition.

Crossplots of the corundum-normalized intensities of calcite versus quartz and chlorite versus illite (Fig. F6) show that all sites share a similar lithology; no site-specific clusters or trends are displayed. An exception is Site U1325 with generally higher quartz contents than the other sites, which is explained by the high abundance of coarse-grained turbidites. Although the abundances of illite and chlorite are positively correlated, suggesting a common detrital origin, quartz and calcite intensities are uncorrelated, likely because the calcite is a mixture of detrital, biogenic, and authigenic origins.